Isoseismal map

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Isoseismal map for the 1968 Illinois earthquake 1968 Illinois earthquake.svg
Isoseismal map for the 1968 Illinois earthquake

In seismology, an isoseismal map is used to show lines of equally felt seismic intensity, generally measured on the Modified Mercalli scale. Such maps help to identify earthquake epicenters, particularly where no instrumental records exist, such as for historical earthquakes. They also contain important information on ground conditions at particular locations, the underlying geology, radiation pattern of the seismic waves, and the response of different types of buildings. They form an important part of the macroseismic approach, i.e. that part of seismology dealing with noninstrumental data. The shape and size of the isoseismal regions can be used to help determine the magnitude, focal depth, and focal mechanism of an earthquake. [1] [2]

Contents

History

The first known isoseismal map was produced for the 1810 earthquake in Mór in Hungary, and published by Kitaibel and Tomtsányi in 1814. [3] The first, six-level intensity scale was proposed by Egen in 1828 for an earthquake in Rhineland. [4] [5] Robert Mallet coined the term "isoseismal" and produced a map for the 1857 Basilicata earthquake with a three-fold intensity scale and used this and other information to identify the epicentral area (a term he also coined). [6] Later studies made use of similar techniques, the main changes being to the actual seismic intensity scale employed.

Methodology

Firstly, observations of the felt intensity need to be obtained for all areas affected by the tremor. In the case of recent earthquakes, news reports are augmented by sending out questionnaires or by collecting information online about the intensity of the shaking. For a historical earthquake, the procedure is much the same, except that it requires searching through contemporary accounts in newspapers, letters, diaries, etc. Once the information has been assembled and intensities assigned at the location of the individual observations, these are plotted on a map. Isoseismal lines are then drawn to link together areas of equal shaking. Because of local variations in the ground conditions, isoseismals generally separate zones of broadly similar felt intensity, while containing areas of both higher and lower degrees of shaking. [1] To make the isoseismals less subjective, attempts have been made to use computer-based methods of contouring such as kriging, rather than relying on visual interpolation. [2] [7]

Use

Locating the epicenter

In most earthquakes, the isoseismals define a single clear area of maximum intensity, which is known as the epicentral or meizoseismal area. [8] In some earthquakes, more than one maximum exists because of the effect of ground conditions or complexities in the rupture propagation, and other information is, therefore, required to identify the area that contains the epicenter.

Measuring the magnitude

The magnitude of an earthquake can be estimated by measuring the area affected by intensity level III or above in km2 and taking the logarithm. [1] A more accurate estimate relies on the development of regional calibration functions derived using many isoseismal radii. [7] Such approaches allow magnitudes to be estimated for historical earthquakes.

Estimating the focal depth

The depth to the hypocenter can be estimated by comparing the sizes of different isoseismal areas. In shallow earthquakes, the lines are close together, while in deep events the lines are spread further apart. [9]

Confirming the focal mechanism

Focal mechanisms are routinely calculated using teleseismic data, but an ambiguity remains as two potential fault planes always are possible. The shape of the areas of highest intensity are generally elongated along the direction of the active fault plane.

Testing seismic hazard assessments

Because of the relatively long history of macroseismic intensity observations (sometimes stretching back many centuries in some regions), isoseismal maps can be used to test seismic hazard assessments by comparing the expected temporal frequency of different levels of intensity, assuming an assessment is true and the observed rate of exceedance. [10]

Related Research Articles

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The 1872 North Cascades earthquake occurred at 9:40 p.m. local time on December 14 in central Washington Territory. A maximum Mercalli intensity of VIII (Severe) was assessed for several locations, though less intense shaking was observed at many other locations in Washington, Oregon, and British Columbia. Some of these intermediate outlying areas reported V (Moderate) to VII shaking, but intensities as high as IV (Light) were reported as far distant as Idaho and Montana. Due to the remote location of the mainshock and a series of strong aftershocks, damage to structures was limited to a few cabins close to the areas of the highest intensity.

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The 1969 Sharm El Sheikh earthquake occurred on March 31 off the southern Sinai Peninsula in northeastern Egypt. The epicenter was located near Shadwan island, southwest of the city of Sharm El Sheikh, at the confluence of the Red Sea and the Gulf of Suez. This normal-slip shock measured 6.6 on the moment magnitude scale, had a maximum reported intensity of VII on the Mercalli intensity scale, and was responsible for several deaths and injuries.

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The 1912 Maymyo earthquake or Burma earthquake struck Burma on the morning of May 23, with an epicentre near Taunggyi and Pyin Oo Lwin in Shan State. The earthquake was initially calculated at 8.0 on the surface wave magnitude scale (Ms ) by Beno Gutenberg and Charles Francis Richter, and described by them as being one of the most remarkable seismic events in the early 1900s. Recent re-evaluation of the earthquake, however, have revised the magnitude to 7.6–7.9. It was preceded by two foreshocks on May 18 and 21 with respective intensities V and VII on the Rossi–Forel scale, while the mainshock was assigned IX. Shaking was felt throughout most of Burma, parts of Siam and Yunnan; an area covering approximately 375,000 square miles. It was one of the largest earthquakes in the country.

An earthquake occurred at 2:13 p.m. on Friday, July 19, 2019, and affected millions of many in the middle of the day. Several seismological institutes determined a magnitude of about 5.3 and the epicentral region appeared to be south of Mt Parnitha, ~20 km NW of the Athens metropolitan area. Nearly 20 years before, on the 7th September 1999, Athens was struck by a 6.0 magnitude earthquake.

The 1984 Cachar earthquake rattled much of Southern Assam on December 31, 1984, at 5:03 a.m. (UTC+5:30) with an epicenter 20 kilometers southwest of Lakhipur. The quake measured with a magnitude of 6.0 on the moment magnitude scale and an estimated intensity of VIII (Severe) on the Modified Mercalli intensity scale. About 20 people died and 100 others sustained mild to severe injuries.

The 1979 Saint Elias earthquake occurred near noon local time on the 28th of February. It measured Mw 7.4–7.6. Though the maximum recorded Modified Mercalli intensity was VII, damage was minimal and there were no casualties due to the remoteness of the faulting. The epicenter lies near the Alaskan border between America and Canada.

References

  1. 1 2 3 How to map an earthquake, by Roger Musson, BGS
  2. 1 2 Linkimer, L. 2008. Application of the kriging method to draw isoseismal maps of the significant 2002–2003 Costa Rican earthquakes. Revista Geológica de América Central, 38, 119–134. Archived 2010-08-06 at the Wayback Machine
  3. ↑ Varga, P. (2008). "History of Early Isoseismal Maps". Acta Geodaetica et Geophysica Hungarica. 43 (2–3): 285–307. doi:10.1556/AGeod.43.2008.2-3.15. S2CID   128898064.
  4. ↑ Oldroyd, D.; Amador, F.; Kozak, J.; Carneiro, A.; Pinto, M. (2007). "The Study of Earthquakes in the Hundred Years Following the Lisbon Earthquake of 1755". Earth Sciences History. 26 (3): 321–370. doi:10.17704/eshi.26.2.h9v2708334745978. Archived from the original on 2012-07-11.
  5. ↑ Egen, P. N. C. (1828). "Über das Erdbeben in den Rhein-und Niederlanden vom 23. Februar 1828". Annalen der Physik und Chemie. 13 (5): 153–163. Bibcode:1828AnP....89..153E. doi:10.1002/andp.18280890514.
  6. ↑ Robert Mallet (1862). Great Neapolitan Earthquake of 1857: The First Principles of Observational Seismology as Developed in the Report to the Royal Society of London of the Expedition Made by Command of the Society Into the Interior of the Kingdom of Naples, to Investigate the Circumstances of the Great Earthquake of Demember 1857. Royal Society.
  7. 1 2 Ambraseys, N. N.; Douglas, J. (2004-10-01). "Magnitude calibration of north Indian earthquakes". Geophysical Journal International. 159 (1): 165–206. Bibcode:2004GeoJI.159..165A. doi: 10.1111/j.1365-246X.2004.02323.x . ISSN   0956-540X.
  8. ↑ Ambraseys, N.N.; Melville, C.P. (2005). A History of Persian Earthquakes. Cambridge University Press. pp. xiii. ISBN   9780521021876.
  9. ↑ Mahajan, A. K.; Kumar, N.; Arora, B. (2006), "Quick Look Isoseismal Map of 8 October 2005 Kashmir Earthquake" (PDF), Current Science, 91 (3): 356–361, JSTOR   24094145
  10. ↑ Pecker, Alain; Faccioli, Ezio; Gurpinar, Aybars; Martin, Christophe; Renault, Philippe (2017). An Overview of the SIGMA Research Project. Geotechnical, Geological and Earthquake Engineering. Springer International Publishing. pp. 141–146. doi:10.1007/978-3-319-58154-5_8. ISBN   9783319581538.
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